The Total Myth of Ocean Acidification, Part Deux: The Scientific Basis

The Total Myth of Ocean Acidification, Part Deux: The Scientific Basis

Guest essay by David Middleton

Here’s a shocker… I’ve actually never seen Hot Shots! Part Deux.  As much as I love stupid comedies, I’ve never actually seen the movie.  But I do love to use the “part deux” bit… and part trois, quatre, etc.  Anyway, I digress…  In part one, we discussed the evolution of the phrase “ocean acidification.”  In part deux, we will examine the scientific basis of the myth.

What’s that? How can a myth have a scientific basis?  Lots of myths have a scientific, historical and/or otherwise factual basis.  This Smithsonian article lists the geological inspirations of ten myths.  They could easily add the myth of “ocean acidification” to this list.

Warning: This is a long post… 6178 words.

Part Deux-Point-Un: Chicken Little of the Sea visits the Paleocene-Eocene Thermal Maximum

The Paleocene-Eocene Thermal Maximum (PETM) was literally a period of “hell on Earth,” mass extinctions, oceans of battery acid, “human sacrifice, dogs and cats living together… mass hysteria!”

As you can see from this marine biodiversity graph, life on Earth nearly ceased to exist 55.5 million years ago…


Figure 1.  The five real mass extinction events are numbered 1-5.  Each is accompanied by a sharp drop in marine biodiversity.  Cambrian fauna = yellow, Paleozoic fauna = green, Modern fauna = blue, and soft bodied organisms = purple.  Note the total lack of a dip anywhere in the Tertiary Period.  “Redrawn from Sepkoski, J.J. Jr, 1984, A kinetic model of Phanerozoic taxonomic diversity, III.
Post Paleozoic families and mass extinctions: Paleobiology 10:246-267.” SEPM Strata

Oh, wait a second… scratch all that, I was thinking of the Permian-Triassic mass extinction event.  Just in case anyone failed to notice: /SARC.

What do we know about the PETM?

  • It occurred about 55.5 million years ago and lasted about 220,000 years.
  • It got really hot.  The PETM may have been the second hottest phase of the Cenozoic Era.  Although it got hotter, for a longer period of time 50-53 million years ago, the Early Eocene Climatic Optimum (EECO) doesn’t get much press.  You can see where I had to “white out” an arrow pointing at the EECO because it wasn’t the PETM.

Figure 2.  Cenozoic temperature change.  Funny how the PETM is often cited as a nightmarish version of a real-world RCP8.5… While the warmer EECO is a climatic optimum. (Zachos et al., 2001)

  • The lysocline shoaled by as much as 500 to more than 2,000 meters.  I’ll explain shoaling of the lysocline later on in this post.
  • There was a fairly significant extinction of benthic (the bottom of the water, irrespective of depth) foraminifera (marine calcifier bugs used for stratigraphic correlation).

What does the so-called consensus say happened during the PETM?

  • A sudden rise in atmospheric CO2 and/or CH4 drove this warming.




Figure 3.  Cenozoic CO2 atmospheric mixing ratio and seawater partial pressure.  Notice the huge difference between atmospheric CO2 and pCO2.  Also notice that pCO2 was higher before and after the PETM and that stomata data indicate that CO2 was about what it is today, apart from a short duration spike to about 800 ppmv 55.2 Mya.  Talk about settled science!

  • The oceans acidified.  From 60 to 50 million years ago it has been estimated that seawater pH ranged from 7.42 to 7.92 (Pearson et al., 2000)… Hardly acidic, the PETM wasn’t even the lowest pH value of the Paleocene-Eocene epochs.  The EECO actually exhibited a lower pH.
    • The PETM is often cited as a geological analogy for the modern myth of ocean acidification… It’s a great example of the scientific basis of the myth.

Figure 4.  Cenozoic seawater pH from boron isotopes in planktonic foraminifera (modified after Pearson & Palmer, 2000). Note that pH was lower than the PETM 51.5 (EECO) and 59.5 Mya.

  • A mass extinction occurred.
    • Laughable… Really laughable.
    • The Lower Tertiary period (Paleocene + Eocene epochs) was a time of booming biodiversity, particularly in the tropics.

Figure 5. Cenozoic biodiversity of Amazonia (Hoorn et al., 2010).  Rain forests must like “ocean acidification.”

Shoaling of the Lysocline?  What’s a Lysocline?

I doubt I’m the only 1970’s-educated geologist who reacts to the phrase “ocean acidification” by rolling his eyes and shouting, “It’s called shoaling of the lysocline, the oceans can’t acidify!”  First, a couple of definitions from the Society for Sedimentary Geology (SEPM, formerly known as the Society of Economic Paleontologists and Mineralogists)…

Oceanographic Setting
The deposition of carbonate material depends on the oceanographic setting of the area; this includes the water chemistry, water depth, and the hydrography of the area. The carbonate slope is a very dynamic region, each of which experiences different amounts of light, nutrients, temperature, pressure, chemistry, and biota.

Ocean Chemistry:
Lysocline: the depth at which a rapid increase in dissolution occurs; it separates the well preserved (above) from the poorly preserved (below) calcareous microfossil assemblages . The typical depth of the lysocline is between 3700-4500m and varies are a result of the carbonate ion concentration in the deep and intermediate water masses. It is shallowest when the CO2 concentration of the water is highest because those waters are the most corrosive to the calcareous microfossils.

Compensation Depth (of aragonite or calcite): the depth at which the amount of calcium carbonate delivered to the seafloor is equal to the amount removed by dissolution. The average depth of the calcite compensation depth (CCD) is 4500 m in the Pacific and 5500 m in the Atlantic and shallows when there is a greater supply of carbonate material to the seafloor. Only above the CCD can carbonate materials be deposited (below the CCD they dissolve and do not reach the sea floor).  The deep depth of the CCD results only in dissolution on the lower parts of the slope.

Factors that affect the depth of the lysocline and the compensation depth include:

  • Water temperature
  • Depth
  • CO2 concentration
  • pH (high pH values aid in carbonate preservation)
  • Amount of carbonate sediment supply
  • Amount of terrigenous sediment supply

Calcium carbonate solubility increases with increasing carbon dioxide content, lower temperatures, and increasing pressure.  Other factors that can influence the dissolution of calcium carbonate: organic coatings on the grains, size of the grain (smaller grains dissolve faster).

SEPM Strata


Did you know…

Without calcite and aragonite many of Earth’s organisms could not exist. These are the minerals most invertebrate organisms use to construct their shells and hard parts. So if you have ever admired a colorful seashell, you have already paid tribute to the range of colors calcite and aragonite come in and indirectly to the ease with which calcite and aragonite form at the Earth’s surface.

Aragonite and calcite are ‘polymorphs’, minerals that have the same chemical composition but slightly different crystal structures. Both minerals can occur together and are so similar to one another that distinguishing between them is seldom important to anyone but a professional geologist. Calcite is more stable and common than aragonite under the chemistry of our modern seas, but at times in the Earth’s past, aragonite was the more stable and common form. The two minerals are nearly identical in their physical properties, so through the remainder of this website they will be treated together under the name ‘calcite’.

Calcite forms in a range of settings from hot springs and underground caverns to growing coral reefs and seashells. This not only reflects calcite’s abundance, but also the ease with which it forms, dissolves, and reforms. Calcite is almost as common in our society as it is in nature, its uses ranging from medicine and animal feed, to Michelangelo’s ‘Pieta,’ and highway overpasses. To a remarkable degree, human society mimics marine organisms in the sense that we rely on calcite to construct many of the ‘hard’ parts of our society, in the form of marble, plaster, mortar, and cement.

Description and Identifying Characteristics

Calcite occurs in both crystalline and massive forms. Crystals of calcite are usually transparent to translucent, but can exhibit a wide variety of colors if the crystal includes minor impurities. Masses of calcite also tend to be light colored, but as with the transparent crystals, the presence of even minor amounts of impurities can create a wide range of colors.

Since calcite can have so many appearances, the simplest way to determine whether a sample contains calcite is to test its reaction to a dilute acid like household vinegar. Calcite will readily react with acid to ‘effervesce’, producing small bubbles of CO2 similar to those formed when you open a bottle of soda and pour it into a glass. Soft enough to be easily scratched by a nail, calcite crystals can also be identified by their rhombic cleavage. ‘Rhombic cleavage’ means that calcite crystals break along parallel planes of weakness that meet at the same angles as a rhomb’s sides.

University of Minnesota

The “lysocline” is the depth below which a rapid dissolution of carbonate material occurs.

The “carbonate compensation depth” (CCD) is the depth at which the deposition and dissolution of carbonate material are equal.

The depths of the lysocline and CCD are controlled by:

  • Water temperature
    • Warming deepens the lysoclne & CCD
  • Depth (pressure)
  • CO2 concentration
    • Increasing CO2 concentration shoals (makes shallower) the lysocline & CCD
  • pH (high pH values aid in carbonate preservation)
    • Lowering pH shoals the lysocline & CCD
  • Amount of carbonate sediment supply
    • Increasing carbonate sediment supply deepens the lysocline & CCD
  • Amount of terrigenous sediment supply

The “bad news” here for the Warmunists is that warming water and increased carbonate sediment supply tend to offset the effects of lowering pH and increasing pCO2.  The really bad news for the Warmunists is that the dissolution of benthic and planktic formaminfera is a great source of carbonate sediment supply:

Studies of modern carbonate settings have documented varied origins for mud-size sediment, including disintegration of benthic and planktic organisms, precipitation from the water column, and mechanical breakdown of larger particles. Carbonate muds accumulate in protected “low-energy” settings on the platform top and are also exported to adjacent deeper-water settings.

Harris & Katz, 2008

Shoaling of the Lysocline during the PETM

There is extensive evidence for a shoaling of the lysocline during the PETM.

The Paleocene/Eocene Thermal Maximum (PETM) was a transient interval of global warming ~55 m.y. ago associated with transformation of ecosystems and changes in carbon cycling. The event was caused by the input of massive amounts of CO2 or CH4 to the ocean-atmosphere system. Rapid shoaling of the lysocline and calcite compensation depth (CCD) is a predicted response of CO2 or CH4 input; however, the extent of this shoaling is poorly constrained. Investigation of Ocean Drilling Program (ODP) Sites 1209–1212 at Shatsky Rise, which lies along a depth transect, suggests a minimum lysocline shoaling of ~500 m in the tropical Pacific Ocean during the PETM. The sites also show evidence of CaCO3 dissolution within the sediment column, carbonate “burn-down” below the level of the carbon isotope excursion, and a predicted response to a rapid change in deepwater carbonate saturation.  Close examination of several foraminiferal preservation proxies (i.e., fragmentation, benthic/planktonic foraminiferal ratios, coarse fraction, and CaCO3 content) and observations of foraminifers reveal that increased fragmentation levels most reliably predict intervals with visually impoverished foraminiferal preservation as a result of dissolution. Low CaCO3 content and high benthic/planktonic ratios also mirror intervals of poorest preservation.

Colosimo, Bralowe & Zachos, 2006

This is what the PETM shoaling of the lysocline looked like:


Figure 6.  About 20 cm of sediment with a δ13C depletion, decrease in CaCO3 and an increase in fragmented benthic foram tests… Scary? LOL!



This paper was initially submitted for publication in March 2004… Can anyone guess what phrase did not appear in this 36-page paper?  You got it!  “Ocean acidification” was never mentioned in this paper or most other PETM papers prior to Ken Caldeira’s fabrication of the mythical phrase in 2003.  Since then, it has become ubiquitous.

PETM Benthic Foraminifera “Mass Extinction”

If benthic foraminifera were driven to extinction by the PETM ocean acidification, why do we still have benthic foram’s today?  The Permian-Triassic mass extinction took out trilobites… They didn’t come back.  The K-Pg (K-T) mass extinction wiped out all of the remaining dinosaurs… Apart from Jurrasic Park and Barney, they have remained extinct.  However, those rascally benthic foram critters just wouldn’t stay extinct (Yes… I am being a smartass).

In the Plio-Pleistocene and Miocene “rocks” of the Gulf of Mexico, we rely on the extinctions of benthic & planktonic foram’s and other calcareous nanofossils for chrono- and bio-stratigraphic correlations.  Unlike “hard rocks” of the Mesozoic in places like East Texas, we don’t have “rock formations” as they are commonly understood.  We need foram extinctions in order to correlate wells.  So… The more foram extinctions, the better.

Here’s a Paleogene biostratigraphic chart of the US Gulf Coast Basin from Paleo-Data®, Inc.


Figure 7.  Paleogene biostratigraphic chart of the US Gulf Coast Basin. Click here for large PDF.

The far-right column is titled “Benthic Foraminifera.”  This symbol next to a bug name: ▼, indicates a “last appearance datum.”  Of course, since the well is being drilled from the top-down, it’s the first appearance of that particular bug in the well.  Unfortunately for the bugs, they were deposited from the bottom-up.  A last appearance datum generally indicates the extinction of that particular bug.  However, there’s never a shortage of bugs because new ones evolve all the time.

Here’s a “funny thing” about the PETM benthic foraminifera “mass extinction”: The benthic foram’s rapidly recovered from their extinction (literally):

Palaeogeography, Palaeoclimatology, Palaeoecology 279 (2009) 186–200.

Extinction and recovery of benthic foraminifera across the Paleocene–Eocene Thermal Maximum at the Alamedilla section (Southern Spain)

L. Alegret , S. Ortiz E., Molina

A b s t r a c t

A complete succession of lower bathyal–upper abyssal sediments was deposited across the Paleocene–Eocene Thermal Maximum (PETM) at Alamedilla (Betic Cordillera, Southern Spain), where the benthic foraminiferal turnover and extinction event associated with the negative carbon isotope excursion (CIE) across the PETM have been investigated. Detailed quantitative analyses of benthic foraminifera allowed us to distinguish assemblages with paleoecological and paleoenvironmental significance: pre extinction fauna, extinction fauna, survival fauna (including disaster and opportunistic fauna) and recovery fauna. These assemblages have been associated with significant parts of the δ13C curve for which a relative chronology has been established. The correlation between the benthic turnover, the δ13C curve, the calcite and silicate mineral content, and sedimentation rates, allowed us to establish the sequence of events across the PETM. At Alamedilla, the benthic extinction event (BEE) affected ~37% of the species and it has been recorded over a 30-cm-thick interval that was deposited in c.a. 10 ky, suggesting a gradual but rapid pattern of extinction. The beginning of the BEE coincides with the onset of the CIE (+0 ky) and with an interval with abundant calcite, and it has been recorded under oxic conditions at the seafloor (as inferred from the benthic foraminiferal assemblages and the reddish colour of the sediments). We conclude that dissolution and dysoxia were not the cause of the extinctions, which were probably related to intense warming that occurred before the onset of the CIE.

The BEE is immediately overlain by a survival interval dominated by agglutinated species (the Glomospira Acme). The low calcite content recorded within the survival interval may result from the interaction between dilution of the carbonate compounds by silicicate minerals (as inferred from the increased sedimentation rates), and the effects of carbonate dissolution triggered by the shoaling of the CCD.  We suggest that Glomospira species (disaster fauna) may have bloomed opportunistically in areas with methane dissociation, in and around the North Atlantic. The disaster fauna was rapidly replaced by opportunistic taxa, which point to oxic and, possibly, oligotrophic conditions at the seafloor. The CCD gradually dropped during this interval, and calcite preservation improved towards the recovery interval, during which the δ13C values and the calcite content recovered (c.a. +71.25 to 94.23 ky) and stabilized (N94.23 ky), coeval with a sharp decrease in sedimentation rates.

Alegret, Otriz & Molina 2009

Benthic foram’s appear to have an even higher recovery rate from extinction than the Incilius genus of toads

Fig 3 from Extinction and recovery of benthic foraminifera across the Paleocene–EoceneFig 3 from Extinction and recovery of benthic foraminifera across the Paleocene–Eocene

Figure 8.  This provides an entirely different perspective on the word extinction.  Alegret, L., S. Ortiz & E. Molina.  Extinction and recovery of benthic foraminifera across the Paleocene–Eocene
Thermal Maximum at the Alamedilla section (Southern Spain).  Palaeogeography, Palaeoclimatology, Palaeoecology 279 (2009) 186–200

The “ocean acidification” (shoaling of the lysocline) of the PETM is represented by the 30 cm thick band of red clay from 13.4 to 13.7 m on the lithology column in figure 8.  When the lysocline and carbonate compensation depth (CCD)  briefly shoaled, the transition from calcareous to siliceous ooze moved shoreward.  When the CCD dropped back down to its pre-PETM depth, the transition from calcareous to siliceous ooze moved seaward… Leaving a 30 cm thick layer of red clay in the middle of a thick marl sequence.  Rising and falling sea level could have left a similar layer of red clay.

Screen Shot 2015-04-16 at 9.24.26 PMScreen Shot 2015-04-16 at 9.24.26 PM

Figure 9.  “Schematic cross section of the ocean showing different depositional zones based on the calcite compensation depth (Nichols, 2009).” WVU GEOL 616

The benthic foram’s above and below the red clay horizon ceased to exist at that location for about 70,000 to 220,000 years.  However, the fact that at least some of them returned to that location after the PETM might indicate that the benthic foram “mass extinction” was more of a benthic foram depositional “mass relocation,” rather than a true extinction.  I’ll let “Farmer Fran” explain how the benthic foram’s in figure 8 recovered from extinction:

Some authors actually have seriously referred to the PETM benthic foram extinction as a “mass extinction”… And they still expect to be taken seriously?

Excessive carbonate undersaturation of the deep ocean would likely impede calcification by marine organisms and therefore is a potential contributing factor to the mass extinction of benthic foraminifera at the P-E boundary.  Although most plankton species survived, carbonate ion changes in the surface ocean might have contributed to the brief appearance of weakly calcified planktonic foraminifera (6) and the dominance of heavily calcified forms of calcareous algae (37). What, if any, implications might this have for the future? If combustion of the entire fossil fuel reservoir (~4500 GtC) is assumed, the impacts on deep-sea pH and biota will likely be similar to those in the PETM. However, because the anthropogenic carbon input will occur within just 300 years, which is less than the mixing time of the ocean (38), the impacts on surface ocean pH and biota will probably be more severe.

Zachos et al., 2005

Good fracking grief!!!  WTF is “the entire fossil fuel *reservoir*”?  Last I checked, most fossil fuel (coal) isn’t in a reservoir (coal bed methane isn’t a coal reservoir) and the fossil fuels that do occupy reservoirs (petroleum and natural gas) occupy many thousands thousands of different reservoirs.

Accuracy not withstanding… So, if we burned all of the fossil fuels that Zachos et al think exist, the effects on deep-sea biota might be as bad as the PETM and the surface effects might be worse… if we burn all of those fossil fuels within 300 years.  And?  What’s the problem here?  Is the field of speculative non sequitur reasoning now an academic discipline of science?  Oh wait… Yes it is.  It’s what climate science has become since 1988.

Here are Cenozoic temperatures, CO2 and pH plotted all together:




Figure 10.  Cenozoic Triple Crown: Temperature, CO2 and pH.  There is no similarity between the modern world and the PETM.  Anyone who asserts a similarity really needs to clean their crack pipe.

What caused the PETM non-catastrophe?

Well… It certainly wasn’t SUV’s or coal-fired power plants.  The most likely explanation is the formation of the North Atlantic Igneous Province.

During the Paleocene-Eocene thermal maximum (PETM) (1), the sea surface temperature rose by 5°C in the tropics (2) and more than 6°C in the Arctic (3), in conjunction with ocean acidification (4) and the extinction of 30 to 50% of deep-sea benthic formaminiferal species (5). The initiation of the PETM is marked by an abrupt decrease in the δ13C proportion of marine and terrestrial sedimentary carbon (1, 6), which is consistent with the rapid addition of >1500 gigatons of 13C depleted carbon, in the form of carbon dioxide and/or methane, into the hydrosphere and atmosphere (7). The PETM is thought to have lasted only 210,000 to 220,000 years, with most of the decrease in δ13C occurring over a 20,000-year period at the beginning of the event (8).

A possible trigger for the initiation of the PETM is a period of intense flood basalt magmatism attending the opening of the North Atlantic (9, 10), by generating metamorphic methane from sill intrusion into basin-filling carbon-rich sedimentary rocks (11).Here we present 40Ar/39Ar age determinations that allow the correlation of Early Tertiary volcanic rocks of East Greenland and the Faeroe Islands with the Danish Ash-17 deposit, which closely overlies PETM sequences in the North Atlantic. In East Greenland, a >5-km thick sequence of plateau basalts formed in 1.0 ±0.5 million years (My).  A surge in magma production, coupled with the eruption of mid-ocean ridge basalt (MORB)–like flows in the lower part of the flood basalt sequence, indicates the initiation of seafloor spreading at 55.5 ± 0.3 million years ago (Ma). The onset of the PETM correlates closely with this breakup-related magmatism.

Storey, Duncan & Swisher, 2008


The “mass extinction” of benthic foram’s was limited to “30 to 50% of deep-sea benthic formaminiferal species,” some of which appear to have un-extincted after the PETM… Bravo Foxtrot Delta.

The trigger could have been “the rapid addition of >1500 gigatons of 13C depleted carbon, in the form of carbon dioxide and/or methane, into the hydrosphere and atmosphere… over a 20,000- year period at the beginning of the event.”  

Over the past 266 years, humans have added about 432 gigatons of 13C depleted carbon, in the form of carbon dioxide and/or methane, into the hydrosphere and atmosphere, nearly 1/3 of the PETM in a fraction of the time and there’s no actual evidence that we have significantly shoaled the lysocline.

The funniest “funny thing” about the PETM and other early Paleogene climatic optima is that they may very well have been “astronomically paced” (Lourens et al., 2005).  It makes one wonder if plate tectonics might also be influenced by astronomical pacing… But that’s a whole other area of speculation.  If the PETM, EECO, MECO, etc. were actually driven by orbital mechanics…



Mythical evidence for shoaling of the Lysocline during the equally mythical “Anthropocene”

According to Feely et al, 2004, the supersaturation/undersaturation horizons for aragonite and calcite have shoaled over the course of the mythical geologic epoch known as the “Anthropocene.”

Pages from Feely et al 2004Pages from Feely et al 2004

Figure 11. “Anthropocene” shoaling of the calcite and aragonite compensation depths… Not measured… Calculated from CO2. 1 decibar [dbar] = 1 meter sea water [msw]. Can you say “insignificant relative to the PETM shoaling?” From Feely et al., 2004.

From Feely et al., 2012…

Over the past 250 years, since the beginning of the industrial revolution, there has been about a 16% decrease in aragonite and calcite saturation state in the Pacific Ocean. From repeat oceanographic surveys, we have observed an average 0.34% yr−1 decrease in the saturation state of surface seawater with respect to aragonite and calcite over a 14‐year period. This has caused an upward migration of the aragonite and calcite saturation horizons toward the ocean surface on the order of 1–2 m yr−1. These changes are the result of the uptake of anthropogenic CO2 by the oceans, as well as other smaller scale regional changes in circulation over decadal time scales. If CO2 emissions continue as projected out to the end this century, the resulting changes in the marine carbonate system would mean that many coral reef systems in the Pacific would probably no longer be able to maintain the necessary rate of calcification required to sustain their vitality.

Feely et al., 2012

The 16% decrease in aragonite and calcite saturation state in the Pacific Ocean over the past 250 years is entirely based on calculating the preindustrial aragonite and calcite from the assumed preindustrial atmospheric CO2 concentration.  It is circular reasoning.  Regarding that claim that they’ve measured 14-28 m of shoaling over a 14-year period… FOURTEEN YEARS?!?!?

How’s about we have look at a slightly longer measurement record and an actual laboratory experiment?

Part Deux-Point-Deux: Chicken Little of the Sea Revisits Station ALOHA and the WHOI laboratory

Station ALOHA and HOTS

The Hawaii Ocean Time Series (HOTS) is a continuous record of surface (~0-30 m) CO2 measurements that currently runs from Halloween 1988 through Thanksgiving 2016.  HOTS also includes pH, aragonite/calcite saturation, dissolved inorganic carbon (DIC or ), total alkalinity (TA), salinity, temperature and and other measurements.

Station ALOHA
A Long-term Oligotrophic Habitat Assessment
(Station 2: a 10 Km radius circle centered at 22 45’N, 158 W, approximately 100 km north of Oahu, Hawaii).

The HOT Program


Figure 1.  Station ALOHA location map.

All data in this product are from Station ALOHA (22°45’N, 158°00’W). HOT program
background information and details of sampling strategy may be found in Karl and Lukas (1996) and Karl et al. (2001). Results from the HOT CO2 measurement program may be found in Winn et al. (1994, 1998) and Dore et al. (2003, 2009, 2014).

The data in this product represent mean surface (0-30 dbar) values for each HOT cruise except where otherwise indicated.


The Station ALOHA HOTS data can be accessed here.

What do the HOTS data tell us?

There is no sea surface temperature (SST) warming trend at Station ALOHA over the past 29 years and there is a weak trend of increasing salinity.


Figure 2.  Station ALOHA temperature and salinity trends (Oct. 1988 – Nov. 2016).  Adapted from: Dore, J.E., R. Lukas, D.W. Sadler, M.J. Church, and D.M. Karl. 2009. Physical and biogeochemical modulation of ocean acidification in the central North Pacific. Proc Natl Acad Sci USA 106:12235-12240

About half of the Station ALOHA cruises did not actually measure pH.  It was usually calculated.  Seawater pH is usually calculated from DIC and TA because it is not easy to directly obtain meaningful seawater pH measurements.  NOAA/PMEL assess pre-1989 pH measurements as pretty well useless…

The data collected prior to 1989 are typically not well documented and their metadata is incomplete; therefore, such data are of unknown and probably variable quality. The reasons for this are manifold (see next section). The uncertainty of these older pH measurements is rarely likely to be less than 0.03 in pH, and could easily be as large as 0.2 in pH. This data set is thus not at all well-suited to showing a change of 0.1 in pH over the last 100 years — the amount of pH change that would be expected to occur over the 100 years since the first seawater pH measurements, as a result of the documented increase in atmospheric CO2 levels and assuming that the surface ocean composition remains in approximate equilibrium with respect to the atmosphere.

It is only since the 1990s that it has been possible to discern small pH changes in the ocean with reasonable confidence. The figure in Feely (2008, updated version shown above) shows the changes in pH inferred from measured changes in the seawater carbonate system seen off Hawaii since 1988, when a regular time-series study was instituted there using the best available methods for measuring CO2 changes in seawater. A limited number of other time-series stations have shown a similar pattern (Rhein et al., 2013; Bates et al., 2014).


Here is the Station ALOHA calculated pH (normalized to 25 °C) trend.  DIC, TA and pH measurements and calculations are usually normalized to a constant temperature and/or salinity because temperature and salinity have a YUGE effect on DIC, TA and pH.


Figure 3.  Station ALOHA calculated pH (at 25 °C) trend  (Oct. 1988 – Nov. 2016).  Adapted from: Dore, J.E., R. Lukas, D.W. Sadler, M.J. Church, and D.M. Karl. 2009. Physical and biogeochemical modulation of ocean acidification in the central North Pacific. Proc Natl Acad Sci USA 106:12235-12240

While the Station ALOHA pH trend does exhibit a negative slope and correlates well with pCO2 (R² = 0.8646), most of the values fall within 2δ of the 1994-2005 mean.  Over the past 29 years the pH has dropped from 8.1 to 8.1, rounded to 1 decimal place.

Next up: Aragonite (Ωarg) and calcite (Ωcal) saturation states:


Figure 4.  Station ALOHA Aragonite and Calcite saturation state trends (Oct. 1988 – Nov. 2016).   Adapted from: Dore, J.E., R. Lukas, D.W. Sadler, M.J. Church, and D.M. Karl. 2009. Physical and biogeochemical modulation of ocean acidification in the central North Pacific. Proc Natl Acad Sci USA 106:12235-12240

Here are the same trends since May 2000…


Figure 5.  Station ALOHA Aragonite and Calcite saturation state trends (May 2000 – Nov. 2016).  Adapted from: Dore, J.E., R. Lukas, D.W. Sadler, M.J. Church, and D.M. Karl. 2009. Physical and biogeochemical modulation of ocean acidification in the central North Pacific. Proc Natl Acad Sci USA 106:12235-12240

PETM here we come!!! (do I need to put a /Sarc tag here?)

Here’s a funny correlation.  In situ Ωarg and Ωcal vs. pCO2


Figure 6.  Station ALOHA aragonite saturation vs pCO2 in situ.  Adapted from: Dore, J.E., R. Lukas, D.W. Sadler, M.J. Church, and D.M. Karl. 2009. Physical and biogeochemical modulation of ocean acidification in the central North Pacific. Proc Natl Acad Sci USA 106:12235-12240

Station ALOHA pCO2 in situ also correlates very poorly with the saturation states of aragonite (R² = 0.019) and calcite (R² = 0.0541).  I wonder why the in situ pCO2 and pH correlate so poorly with carbonate saturation.  Maybe it has something to do with being in situ.

In situ…

In its original position or place.  Geol: Said specifically of a rock, soil, or fossil, when in the situation in which it was originally formed or deposited.

Dictionary of Geological Terms, American Geological Institute 1976.

In the case of Station ALOHA, in situ means as measured, unadjusted, not normalized, unadulterated.

Note that In situ Ωarg has a much better correlation to SST than to in situ pCO2


Figure 7.  SST vs aragonite saturation.  Adapted from: Dore, J.E., R. Lukas, D.W. Sadler, M.J. Church, and D.M. Karl. 2009. Physical and biogeochemical modulation of ocean acidification in the central North Pacific. Proc Natl Acad Sci USA 106:12235-12240

No wonder they normalize pCO2 to a constant temperature and DIC & TA to a constant salinity.  As in all things related to Gorebal Warming, all other factors must be held equal for the math to work.

Chicken Little of the Sea checks in for some lab work

Here’s the in situ Ωarg vs. pCO2… normalized to 20 °C and the laboratory correlation from Ries et al, 2009 at 25 °C.  The power function was derived from Ries.


Figure 8.  Station Aloha Aragonite saturation vs pCO2 at 20 °C.   Adapted from: Dore, J.E., R. Lukas, D.W. Sadler, M.J. Church, and D.M. Karl. 2009. Physical and biogeochemical modulation of ocean acidification in the central North Pacific. Proc Natl Acad Sci USA 106:12235-12240 and Ries, Justin B., Anne L. Cohen, Daniel C. McCorkle; Marine calcifiers exhibit mixed responses to CO2-induced ocean acidification. Geology ; 37 (12): 1131–1134. doi:

Ries et al., 2009 conducted a laboratory experiment on a representative sample of marine calcifiers (oceanic critters that make shells, tests, carapaces, etc. out of CaCO3)…

To investigate the impact of ocean acidification on a range of benthic marine calcifiers, we reared 18 calcifying species for 60 d in isothermal (25 °C; see the Data Repository for discussion) experimental seawaters equilibrated with average pCO2 values (±SD) of 409 (±6), 606 (±7), 903 (±12), and 2856 (±54) ppm, corresponding to modern pCO2, and ~2, 3, and 10 times pre-industrial levels (~280 ppm), respectively, and yielding average seawater saturation states (±SD) of 2.5 (±0.4), 2.0 (±0.4), 1.5 (±0.3), and 0.7 (±0.2) with respect to aragonite (see the Data Repository for detailed methods). These carbonate system parameters were selected to represent the range of values predicted for the coming millennium (Brewer, 1997; Feely et al., 2004) and to span those reported to have occurred since mid-Cretaceous time (ca. 110 Ma; Royer et al., 2004; Tyrrell and Zeebe, 2004). The organisms’ net rates of calcifi cation (total calcification minus total dissolution) under the various pCO2 treatments were estimated from changes in their buoyant weight and verified with dry weight measurements after harvesting.

Here is my interpretation of Ries’ results (modified after Table 1 and Figure )…

Modern 2x PI 3x PI 10x PI
pCO2 HOTS                    589                    897                 1,542                 6,476
pCO2 Ries                    409                    606                    903                 2,856
ΩARG 2.5 2.0 1.5 0.7
Organism Panel % Below Modern % Below Modern % Below Modern % Below Modern
Blue Crab A 0% 0% 0% 0%
Shrimp B 0% 0% 0% 0%
Lobster C 0% 0% 0% 0%
Limpet D 0% 0% 0% 0%
Purple urchin E 0% 0% 0% 0%
Coralline red algae F 0% 0% 0% 0%
Halimeda G 0% 0% 0% 100%
Blue mussel H 0% 10% 17% 20%
Temp. coral I 0% 0% 0% 14%
Pencil urchin J 0% 0% 0% 100%
Hard clam K 0% 0% 20% 100%
Conch L 0% 50% 25% 100%
Serpulid worm M 0% 0% 22% 30%
Peri-winkle N 0% 0% 25% 44%
Bay scallop O 0% 0% 40% 60%
Oyster P 0% 50% 50% 100%
Whelk Q 0% 40% 0% 100%
Soft clam R 0% 50% 75% 100%

The aragonite saturation data from Station ALOHA indicate that critical levels would occur at much higher pCO2 levels than Ries’ formulations.  Most of the marine calcifier taxa were relatively unaffected below the equivalent of 600-900 ppm CO2.

Taxa without a strong preference for aragonite over calcite, that had a higher degree of organic cover and those that utilized photosynthesis tended to fare better under high COconditions.  Some of the best seafood (crab, shrimp & lobster) thrive in under high COconditions.


Fgure 9.  (Left) Red boxes approximate current calcification rate range.    (Right) Letters indicate the pCO2 level at which the calcification rate drops below the current range.   Adapted from: Dore, J.E., R. Lukas, D.W. Sadler, M.J. Church, and D.M. Karl. 2009. Physical and biogeochemical modulation of ocean acidification in the central North Pacific. Proc Natl Acad Sci USA 106:12235-12240  and Ries, Justin B., Anne L. Cohen, Daniel C. McCorkle; Marine calcifiers exhibit mixed responses to CO2-induced ocean acidification. Geology ; 37 (12): 1131–1134. doi:

The only marine calcifier which appears to be in peril at pCO2 levels likely to be reached in the next few centuries is the soft clam,  Mya arenaria,… And this is fracking HILARIOUS!!!

The high tolerance of environmental factors is reflected in two statements made by
Hidu & Newell (1989) about clam culture: “Mya larvae are among the most hardy that we have reared; one has to work overtime with incompetence to destroy a brood.” and “If Mya are hardy as larvae they are even more hardy as juveniles.”

Strasser, 1998

Do I need to explain this?

Ries et al., 2009 tried as hard as they could to wipe out marine calcifiers with “ocean acidification.”  The only taxa, they were able to even remotely imperil was Mya arenaria (called “steamers” where I grew up)… possibly the hardiest of all hardy marine calcifiers.  This bit can’t be repeated too often…

Mya larvae are among the most hardy that we have reared; one has to work overtime with incompetence to destroy a brood.”

You really couldn’t make this schist up if you were trying.   Mya arenaria is possibly the most successful invasive species of the Phanerozoic Eon… It was an invasive species before Adam met Eve… Long before Adam met Eve.  Yet, it is the only taxa that Ries et al., 2009 managed to “work overtime with incompetence to destroy a brood.”

Oh… And pCO2 is not “well-mixed” like the atmospheric mixing ratio of CO2 .  It varies widely…

So… Chicken Little of the Sea will pretty well only be an issue, where it is already an issue… mostly in areas of strong upwelling.


The Earth isn’t behaving any differently over the past 150 years than it has behaved over the past [fill in the blank] years.  Same as it ever was


Alegret, L., S. Ortiz & E. Molina.  Extinction and recovery of benthic foraminifera across the Paleocene–Eocene Thermal Maximum at the Alamedilla section (Southern Spain).  Palaeogeography, Palaeoclimatology, Palaeoecology 279 (2009) 186–200

Beerling, D. J. & Royer, D. L. Convergent Cenozoic CO2 history. Nature Geosci. 4, 418–420 (2011)

Colosimo, A.B, Bralower, T.J., and Zachos, J.C., 2006. Evidence for
lysocline shoaling at the Paleocene/Eocene Thermal Maximum on Shatsky
Rise, northwest Pacific. In Bralower, T.J., Premoli Silva, I., and Malone, M.J. (Eds.), Proc. ODP, Sci. Results, 198, 1–36

Dore, J.E., R. Lukas, D.W. Sadler, M.J. Church, and D.M. Karl. 2009. Physical and biogeochemical modulation of ocean acidification in the central North Pacific. Proc Natl Acad Sci USA 106:12235-12240

Feely, R. A., C. L. Sabine, K. Lee, W. Berelson, J. Kleypas, V. J. Fabry, and F. J. Millero (2004), Impact of anthropogenic CO2 on the CaCOsystem in the oceans, Science, 305, 362–366, doi:10.1126/science.1097329

Feely, R. A., C. L. Sabine, R. H. Byrne, F. J. Millero, A. G. Dickson, R. Wanninkhof, A. Murata, L. A. Miller, and D. Greeley (2012), Decadal changes in the aragonite and calcite saturation state of the Pacific Ocean, Global Biogeochem. Cycles, 26, GB3001, doi: 10.1029/2011GB004157.

Harris,  Paul M. (Mitch) and Barry J. Katz.  Carbonate Mud and Carbonate Source Rocks.  Search and Discovery Article #40305 (2008).  Adapted from poster presentation at AAPG Annual Convention, Calgary, Alberta, June 16-19, 2005.

Hoorn, C., Wesselingh, F.P., ter Steege, H.; Bermudez, M.A., Mora, A., Sevink, J., Sanmartin, I., Sanchez-Meseguer, A., Anderson, C.L., Figueiredo, J.P., et al. Amazonian through time: Andean uplift,climate change, landscape evolution and biodiversity. Science 2010, 330, 927–931

Lourens, L. J., A. Sluijs, D. Kroon, J. C. Zachos, E. Thomas, U. Röhl, J. Bowles, and I. Raffi (2005), Astronomical pacing of late Palaeocene to early Eocene global warming events, Nature, 435, 1083–1087, doi:10.1038/nature03814

Pagani, M., J.C. Zachos, K.H. Freeman, B. Tipple, and S. Bohaty. 2005. Marked Decline in Atmospheric Carbon Dioxide Concentrations During the Paleogene. Science, Vol. 309, pp. 600-603, 22 July 2005.

Pearson, P. N. and Palmer, M. R.: Atmospheric carbon dioxide concentrations over the past 60 million years, Nature, 406, 695–699,, 2000.

Ries, Justin B., Anne L. Cohen, Daniel C. McCorkle; Marine calcifiers exhibit mixed responses to CO2-induced ocean acidification. (2009). Geology ; 37 (12): 1131–1134. doi:

Royer, et al., 2001. Paleobotanical Evidence for Near Present-Day Levels of Atmospheric CO2 During Part of the Tertiary. Science 22 June 2001: 2310-2313. DOI:10.112

Storey, Michael, Robert A. Duncan, Carl C Swisher 2007. Paleocene-Eocene Thermal Maximum and the Opening of the Northeast Atlantic. Science 27 April 2007: 587-589. DOI:10.1126

Strasser M, 1999. Mya arenaria: an ancient invader of the North sea coast. Helgolander Meeresunters 52:309–324.

Tripati, A.K., C.D. Roberts, and R.A. Eagle. 2009.  Coupling of CO2 and Ice Sheet Stability Over Major Climate Transitions of the Last 20 Million Years.  Science, Vol. 326, pp. 1394 1397, 4 December 2009.  DOI: 10.1126/science.1178296

Zachos, J. C., Pagani, M., Sloan, L. C., Thomas, E. & Billups, K. Trends, rhythms, and aberrations in global climate 65 Ma to present. Science 292, 686–-693 (2001).

Zachos, et al., 2005. Rapid Acidification of the Ocean During the Paleocene-Eocene Thermal Maximum. Science 10 June 2005: 1611-1615. DOI:10.1126

Superforest,Climate Change

via Watts Up With That?

Leave a Reply

Fill in your details below or click an icon to log in: Logo

You are commenting using your account. Log Out /  Change )

Google+ photo

You are commenting using your Google+ account. Log Out /  Change )

Twitter picture

You are commenting using your Twitter account. Log Out /  Change )

Facebook photo

You are commenting using your Facebook account. Log Out /  Change )

Connecting to %s